Artifact reduction in iterative inversion of geophysical data

ABSTRACT

Method for reducing artifacts in a subsurface physical properties model ( 120 ) inferred by iterative inversion ( 140 ) of geophysical data ( 130 ), wherein the artifacts are associated with some approximation ( 110 ) made during the iterative inversion. In the method, some aspect of the approximation is changed ( 160 ) as the inversion is iterated such that the artifacts do not increase by coherent addition.

CROSS-REFERENCE TO RELATED APPLICATION

This application is a continuation of U.S. patent application Ser. No.13/045,215, filed Mar. 10, 2011, entitled ARTIFACT REDUCTION INITERATIVE INVERSION OF GEOPHYSICAL DATA and claims the benefit of U.S.Provisional Patent Application 61/332,463, filed May 7, 2010, entitledARTIFACT REDUCTION IN ITERATIVE INVERSION OF GEOPHYSICAL DATA. Theentirety of U.S. patent application Ser. No. 13/045,215 and U.S.Provisional Patent Application 61/332,463 are hereby incorporated byreference herein.

FIELD OF THE INVENTION

The invention relates generally to the field of geophysical prospecting,and more particularly to geophysical data processing. Specifically, theinvention pertains to reducing artifacts in iterative inversion of dataresulting from approximations made in the inversion.

BACKGROUND OF THE INVENTION

Geophysical inversion [1,2] attempts to find a model of subsurfaceproperties that optimally explains observed data and satisfiesgeological and geophysical constraints. There are a large number of wellknown methods of geophysical inversion. These well known methods fallinto one of two categories, iterative inversion and non-iterativeinversion. The following are definitions of what is commonly meant byeach of the two categories:

-   -   Non-iterative inversion—inversion that is accomplished by        assuming some simple background model and updating the model        based on the input data. This method does not use the updated        model as input to another step of inversion. For the case of        seismic data these methods are commonly referred to as imaging,        migration, diffraction tomography or Born inversion.    -   Iterative inversion—inversion involving repetitious improvement        of the subsurface properties model such that a model is found        that satisfactorily explains the observed data. If the inversion        converges, then the final model will better explain the observed        data and will more closely approximate the actual subsurface        properties. Iterative inversion usually produces a more accurate        model than non-iterative inversion, but is much more expensive        to compute.

Two iterative inversion methods commonly employed in geophysics are costfunction optimization and series methods. Cost function optimizationinvolves iterative minimization or maximization of the value, withrespect to the model M, of a cost function S(M) which is a measure ofthe misfit between the calculated and observed data (this is alsosometimes referred to as the objective function), where the calculateddata is simulated with a computer using the current geophysicalproperties model and the physics governing propagation of the sourcesignal in a medium represented by a given geophysical properties model.The simulation computations may be done by any of several numericalmethods including but not limited to finite difference, finite elementor ray tracing. Series methods involve inversion by iterative seriessolution of the scattering equation (Weglein [3]). The solution iswritten in series form, where each term in the series corresponds tohigher orders of scattering. Iterations in this case correspond toadding a higher order term in the series to the solution.

Cost function optimization methods are either local or global [4].Global methods simply involve computing the cost function S(M) for apopulation of models {M₁, M₂, M₃, . . . } and selecting a set of one ormore models from that population that approximately minimize S(M). Iffurther improvement is desired this new selected set of models can thenbe used as a basis to generate a new population of models that can beagain tested relative to the cost function S(M). For global methods eachmodel in the test population can be considered to be an iteration, or ata higher level each set of populations tested can be considered aniteration. Well known global inversion methods include Monte Carlo,simulated annealing, genetic and evolution algorithms.

Local cost function optimization involves:

-   -   1. selecting a starting model,    -   2. computing the gradient of the cost function S(M) with respect        to the parameters that describe the model,    -   3. searching for an updated model that is a perturbation of the        starting model in the gradient direction that better explains        the observed data.        This procedure is iterated by using the new updated model as the        starting model for another gradient search. The process        continues until an updated model is found which satisfactorily        explains the observed data. Commonly used local cost function        inversion methods include gradient search, conjugate gradients        and Newton's method.

As discussed above, iterative inversion is preferred over non-iterativeinversion, because it yields more accurate subsurface parameter models.Unfortunately, iterative inversion is so computationally expensive thatit is impractical to apply it to many problems of interest. This highcomputational expense is the result of the fact that all inversiontechniques require many compute intensive forward and/or reversesimulations. Forward simulation means computation of the data forward intime, and reverse simulation means computation of the data backward intime.

Due to its high computational cost, iterative inversion often requiresapplication of some type of approximation that speeds up thecomputation. Unfortunately, these approximations usually result inerrors in the final inverted model which can be viewed as artifacts ofthe approximations employed in the inversion.

What is needed is a general method of iteratively inverting data thatallows for the application of approximations without generatingartifacts in the resulting inverted model. The present inventionsatisfies this need.

SUMMARY OF THE INVENTION

A physical properties model gives one or more subsurface properties as afunction of location in a region. Seismic wave velocity is one suchphysical property, but so are (for example) density, p-wave velocity,shear wave velocity, several anisotropy parameters, attenuation (q)parameters, porosity, permeability, and resistivity. The invention is amethod for reducing artifacts in a subsurface physical property modelcaused by an approximation, other than source encoding, in an iterative,computerized geophysical data inversion process, said method comprisingvarying the approximation as the iterations progress. In one particularembodiment, the invention is a computer-implemented method for inversionof measured geophysical data to determine a physical properties modelfor a subsurface region, comprising:

(a) assuming a physical properties model of the subsurface region, saidmodel providing values of at least one physical property at locationsthroughout the subsurface region;

(b) selecting an iterative data inversion process having a step whereina calculation is made of an update to the physical properties model thatmakes it more consistent with the measured geophysical data;

(c) making in said calculation an approximation that either speeds upthe selected iterative data inversion process other than by sourceencoding, or that works an accuracy tradeoff;

(d) executing, using the computer, one cycle of the selected iterativedata inversion process with said approximation and using the physicalproperties model;

(e) executing, using the computer, a next iterative inversion cycle,wherein a selection is made to either change some aspect of theapproximation or not to change it;

(f) repeating (e) as necessary, changing the approximation in some orall of the iteration cycles, until a final iteration wherein a selectedconvergence criterion is met or another stopping condition is reached;and

(g) downloading the updated physical properties model from the finaliteration or saving it to computer storage.

In some embodiments of the invention, one or more artifact types areidentified in inversion results as being caused by the approximation,and the aspect of the approximation that is changed in some or alliteration cycles is selected for having an effect on artifacts of theone or more identified artifact types. The effect on artifacts may besuch that artifacts from one approximation do not add constructivelywith artifacts from another iteration cycle that uses an approximationwith a changed aspect.

BRIEF DESCRIPTION OF THE DRAWINGS

The present invention and its advantages will be better understood byreferring to the following detailed description and the attacheddrawings in which:

FIG. 1 is a flow chart showing basic steps in a general method disclosedherein;

FIG. 2 is a flow chart showing basic steps in a particular embodiment ofthe method of FIG. 1 wherein the objective function is approximated byencoding and summing the sources;

FIGS. 3-5 pertain to an example application of the invention embodimentof FIG. 2:

FIG. 3 shows the seismic velocity model from which seismic data werecomputed for the example;

FIG. 4 shows inversion of data from the seismic velocity model in FIG. 3using the inversion method summarized in FIG. 2;

FIG. 5 shows inversion of data from the seismic velocity model in FIG. 3using the inversion method summarized in FIG. 2 without the step inwhich the code used to encode the sources is changed between iterations;

FIG. 6 is a flow chart showing basic steps in a particular embodiment ofthe method of FIG. 1 wherein the approximation is varying the size ofthe grid cells used in the numerical inversion so as to use a fine gridonly where needed;

FIGS. 7-9 pertain to an example application of the invention embodimentof FIG. 6:

FIG. 7 is the seismic velocity model from which seismic data werecomputed for the example;

FIG. 8 shows an inversion of data from the seismic velocity model inFIG. 7 using the inversion method summarized in FIG. 6;

FIG. 9 is an inversion of data from the seismic velocity model in FIG. 7using the inversion method summarized in FIG. 6 without the step inwhich the depth of the artificial reflection generator is changedbetween iterations;

FIG. 10 is a flow chart showing basic steps in a particular embodimentof the method of FIG. 1, wherein the approximation is using only asubset of measured data;

FIGS. 11-13 pertain to an example application of the inventionembodiment of FIG. 10:

FIG. 11 shows the seismic velocity model from which seismic data werecomputed for the example;

FIG. 12 shows an inversion of data from the seismic velocity model inFIG. 11 using the inversion method summarized in FIG. 10; and

FIG. 13 shows an inversion of data from the seismic velocity model inFIG. 11 using the inversion method summarized in FIG. 10 without thestep in which the subset of measured data is changed randomly betweeniterations.

Due to patent constraints, FIGS. 3-5, 7-9, and 11-13 are gray-scaleconversions of color displays.

The invention will be described in connection with its preferredembodiments. However, to the extent that the following detaileddescription is specific to a particular embodiment or a particular useof the invention, this is intended to be illustrative only, and is notto be construed as limiting the scope of the invention. On the contrary,it is intended to cover all alternatives, modifications and equivalentsthat may be included within the scope of the invention, as defined bythe appended claims.

DETAILED DESCRIPTION OF PREFERRED EMBODIMENTS

The present invention is a method for reducing artifacts caused by theapplication of approximations during iterative inversion of geophysicaldata. Geophysical inversion attempts to find a model of subsurfaceproperties that optimally explains observed geophysical data. Theexample of seismic data is used throughout to illustrate the inventivemethod, but the method may be advantageously applied to any method ofgeophysical prospecting and any type of geophysical data. The datainversion is most accurately performed using iterative methods.Unfortunately iterative inversion is often prohibitively expensivecomputationally. The majority of compute time in iterative inversion isspent performing expensive forward and/or reverse simulations of thegeophysical data (here forward means forward in time and reverse meansbackward in time). The high cost of these simulations is partly due tothe fact that each geophysical source in the input data must be computedin a separate computer run of the simulation software. Thus, the cost ofsimulation is proportional to the number of sources in the geophysicaldata, typically on the order of 1,000 to 10,000 sources for ageophysical survey. In typical practice, approximations are appliedduring the inversion to reduce the cost of inversion. Theseapproximations result in errors, or artifacts, in the inverted model.This invention mitigates these artifacts by changing some aspect of theapproximation between iterations of inversion so that the artifactduring one iteration does not add constructively with the artifact inother iterations. Therefore the artifact is reduced in the invertedmodel.

Some common approximations made during iterative inversion that resultin artifacts include:

-   -   1. Processing applied to the measured data    -   2. Inaccurate boundary conditions in the simulation    -   3. Approximations in the simulation (e.g. low order        approximations of derivatives used in the simulator or the size        of the grid cells used in the calculation)    -   4. Approximations in the parameterization of the model (e.g. use        of a spatial grid of parameters that is too coarse to accurately        represent variations in the model).        Two iterative inversion methods commonly employed in geophysics        are cost function optimization and series methods. The present        invention can be applied to both of these methods. A summary of        each of these methods follows next.        Iterative Cost Function Optimization

Cost function optimization is performed by minimizing the value, withrespect to a subsurface model M, of a cost function S(M) (sometimesreferred to as an objective function), which is a measure of misfitbetween the observed (measured) geophysical data and corresponding datacalculated by simulation of the assumed model. A simple cost function Soften used in geophysical inversion is:

$\begin{matrix}{{S(M)} = {\sum\limits_{g = 1}^{N_{g}}\;{\sum\limits_{r = 1}^{N_{r}}\;{\sum\limits_{t = 1}^{N_{t}}\;{{{\psi_{calc}\left( {M,g,r,t,w_{g}} \right)} - {\psi_{obs}\left( {g,r,t,w_{g}} \right)}}}^{N}}}}} & (1)\end{matrix}$where

-   N=norm for cost function (typically the least squares or L2-Norm is    used in which case N=2),-   M=subsurface model,-   g=gather index (for point source data this would correspond to the    individual sources),-   N_(g)=number of gathers,-   r=receiver index within gather,-   N_(r)=number of receivers in a gather,-   t=time sample index within a data record,-   N_(t)=number of time samples,-   ψ_(calc)=calculated geophysical data from the model M,-   ψ_(obs)=measured geophysical data, and-   w_(g)=source signature for gather g, i.e. source signal without    earth filtering effects.

The gathers in Equation 1 can be any type of gather that can besimulated in one run of a forward modeling program. For seismic data,the gathers correspond to a seismic shot, although the shots can be moregeneral than point sources [5]. For point sources, the gather index gcorresponds to the location of individual point sources. For plane wavesources, g would correspond to different plane wave propagationdirections. This generalized source data, ψ_(obs), can either beacquired in the field or can be synthesized from data acquired usingpoint sources. The calculated data ψ_(calc) on the other hand canusually be computed directly by using a generalized source function whenforward modeling (e.g. for seismic data, forward modeling typicallymeans solution of the anisotropic visco-elastic wave propagationequation or some approximation thereof). For many types of forwardmodeling, including finite difference modeling, the computation timeneeded for a generalized source is roughly equal to the computation timeneeded for a point source. The model M is a model of one or morephysical properties of the subsurface region. Seismic wave velocity isone such physical property, but so are (for example) p-wave velocity,shear wave velocity, several anisotropy parameters, attenuation (q)parameters, porosity, and permeability. The model M might represent asingle physical property or it might contain many different parametersdepending upon the level of sophistication of the inversion. Typically,a subsurface region is subdivided into discrete cells, each cell beingcharacterized by a single value of each parameter.

One major problem with iterative inversion is that computing ψ_(calc)takes a large amount of computer time, and therefore computation of thecost function, S, is very time consuming. Furthermore, in a typicalinversion project this cost function must be computed for many differentmodels M.

Iterative Series Inversion

Besides cost function optimization, geophysical inversion can also beimplemented using iterative series methods. A common method for doingthis is to iterate the Lippmann-Schwinger equation [3]. TheLippmann-Schwinger equation describes scattering of waves in a mediumrepresented by a physical properties model of interest as a perturbationof a simpler model. The equation is the basis for a series expansionthat is used to determine scattering of waves from the model ofinterest, with the advantage that the series only requires calculationsto be performed in the simpler model. This series can also be invertedto form an iterative series that allows the determination of the modelof interest, from the measured data and again only requiringcalculations to be performed in the simpler model. TheLippmann-Schwinger equation is a general formalism that can be appliedto all types of geophysical data and models, including seismic waves.This method begins with the two equations:LG=−I  (2)L ₀ G ₀ =−I  (3)where L, L₀ are the actual and reference differential operators, G andG₀ are the actual and reference Green's operators respectively and I isthe unit operator. Note that G is the measured point source data, and G₀is the simulated point source data from the initial model. TheLippmann-Schwinger equation for scattering theory is:G=G ₀ +G ₀ VG  (4)where V=L−L₀ from which the difference between the true and initialmodels can be extracted.

Equation 4 is solved iteratively for V by first expanding it in a series(assuming G=G₀ for the first approximation of G and so forth) to get:G=G ₀ +G ₀ VG ₀ +G ₀ VG ₀ VG ₀+ . . .  (5)Then V is expanded as a series:V=V ⁽¹⁾ +V ⁽²⁾ +V ⁽³⁾+ . . .  (6)where V^((n)) is the portion of V that is n^(th) order in the residualof the data (here the residual of the data is G−G₀ measured at thesurface). Substituting Equation 6 into Equation 5 and collecting termsof the same order yields the following set of equations for the first 3orders:G−G ₀ =G ₀ V ⁽¹⁾ G ₀  (7)0=G ₀ V ⁽²⁾ G ₀ +G ₀ V ⁽¹⁾ G ₀ V ⁽¹⁾ G ₀  (8)0=G ₀ V ⁽³⁾ G ₀ +G ₀ V ⁽¹⁾ G ₀ V ⁽²⁾ G ₀ +G ₀ V ⁽²⁾ G ₀ V ⁽¹⁾ G ₀ +G ₀ V⁽¹⁾ G ₀ V ⁽¹⁾ G ₀ V ⁽¹⁾ G ₀  (9)and similarly for higher orders in V. These equations may be solvediteratively by first solving Equation 7 for V⁽¹⁾ by inverting G₀ on bothsides of V⁽¹⁾ to yield:V ⁽¹⁾ =G ₀ ⁻¹(G−G ₀)G ₀ ⁻¹  (10)V⁽¹⁾ from Equation 10 is then substituted into Equation 8 and thisequation is solved for V⁽²⁾ to yield:V ⁽²⁾ =−G ₀ ⁻¹ G ₀ V ⁽¹⁾ G ₀ V ⁽¹⁾ G ₀ G ₀ ⁻¹  (11)and so forth for higher orders of V.

Equation 10 involves a sum over sources and frequency which can bewritten out explicitly as:

$\begin{matrix}{V^{(1)} = {\sum\limits_{\omega}\;{\sum\limits_{s}\;{{G_{0}^{- 1}\left( {G_{s} - G_{0s}} \right)}G_{0s}^{- 1}}}}} & (12)\end{matrix}$where G_(s) is the measured data for source s, G_(0s) is the simulateddata through the reference model for source s and G_(0s) ⁻¹ can beinterpreted as the downward extrapolated source signature from source s.Equation 10 when implemented in the frequency domain can be interpretedas follows: (1) Downward extrapolate through the reference model thesource signature for each source (the G_(0s) ⁻¹ term), (2) For eachsource, downward extrapolate the receivers of the residual data throughthe reference model (the G₀ ⁻¹(G_(s)−G_(0s)) term), (3) multiply thesetwo fields then sum over all sources and frequencies. The downwardextrapolations in this recipe can be carried out using geophysicalsimulation software, for example using finite differences.

Example Embodiment

The flowchart of FIG. 1 shows basic steps in one embodiment of thepresent inventive method. In step 110, an approximation is selected thatwill improve some aspect of the inversion process. The improvement maybe in the form of a speedup rather than increased accuracy. Examples ofsuch approximations include use of an approximate objective function oruse of an approximation in the simulation software. These approximationswill often be chosen to reduce the computational cost of inversion.However, rather than a computational speed-up, the improvement mayinstead work an accuracy tradeoff, i.e. accept more inaccuracy in oneaspect of the computation in return for more accuracy in some otheraspect. In step 140, an update to an assumed physical properties model120 is generated based on the measured data 130. In step 140 theapproximation chosen in 110 is used to perform the update computations.Using iterative local cost function optimization as an example ofiterative inversion, the “update computations” as that term is usedherein include, without limitation, computing the objective (cost)function, the objective function gradient, and all forward modelingrequired to accomplish the preceding. Step 140 produces an updatedphysical properties model 150, which should be closer to the actualsubsurface properties than were those of the assumed physical propertiesmodel 120. Conventionally this updated physical properties model 150would be further improved by feeding it and the measured data 130 backinto the update method in step 140 to produce a further improvedphysical properties model. This conventional iterative inversion methodhas the disadvantage that any artifacts in the inversion that resultfrom the approximation chosen in step 110 will likely reinforceconstructively in the inversion and contaminate the final invertedresult.

Rather than directly returning to step 140, the present inventive methodinterposes step 160 in which some aspect of the approximation chosen instep 110 is changed in a manner such that the artifact caused by theapproximation will change and therefore not be reinforced by theiterations of step 140. By this means the artifact resulting from theapproximation chosen in step 110 will be mitigated.

Examples of Approximations and Corresponding Artifacts

The following table contains examples of step 110, i.e. ofapproximations that might advantageously be used in data inversion, andthat are suitable (step 160) for application of the present invention.The first column of the table lists approximations that could be usedwith this invention. The second column lists the artifact associatedwith each approximation. The last column lists a feature of theapproximation that could be varied between iterations to cause a changein the artifact between iterations that will cause it to addincoherently to the final inverted model and thus be mitigated.

Approximation Artifact Features to vary Encoded simultaneous Cross-talknoise between Vary the encoding of the source seismic data [6] theencoded sources sources [ref. 6, claim 3] Use of a subset of Footprintsof source Vary randomly the subset measured data position in theinverted of measured data models caused by source positions Imperfectabsorbing Inaccuracy at the edges of Vary the thickness of the boundarycondition in the the inverted models caused absorbing boundary layersimulator by artificial reflections from the edges Use of reflectingInaccuracy at the edges of Vary the reflecting boundaries in thesimulator the inverted models caused boundary condition type byartificial reflections (e.g. vary between Dirchlet from the edges orNeumann boundary conditions) Use of random boundary Inaccuracy at theedges of Vary the distribution of the conditions in the simulator theinverted models caused random boundary [7] by artificial reflectionsfrom the edges Spatial variation of size of Errors at the boundariesVary the location of the grid cells in a finite between changes in theboundaries separating difference simulator grid cell size caused byregions with different grid artificial reflections from cell sizes thoseboundaries Spatial variation of the Errors at the boundaries Vary thelocation of the accuracy of the simulation between changes in theboundaries separating operator simulator's operator regions withdifferent accuracy caused by operator accuracies artificial reflectionsfrom those boundaries Use of a grid cell size in Spatial discretizationVary the grid cell size or the simulation that is too errors the originof the grid coarse to accurately represent variations in the model Useof a large time step in Discretization errors Vary the time stepinterval a time domain simulatorThe above list is not exhaustive. The list includes examples only ofapproximations that reduce computation time. Sometimes it isadvantageous to trade inaccuracy in one area to gain more accuracy inanother. An example of such an accuracy tradeoff type of approximationis to use less accurate absorbing boundary conditions in the forwardmodeling in order to make the gradient computations more accurate.Absorbing boundary conditions are needed to solve the differentialequation(s) governing the wave propagation, e.g. the anisotropicvisco-elastic wave propagation equation (or some approximation thereof)in the case of seismic data, or Maxwell's equations in the case ofelectromagnetic data. In general, an accuracy tradeoff involvessacrificing accuracy in one aspect of the method in return for increasedaccuracy in another aspect.

Test Example 1 Encoded Objective Function

FIGS. 2-5 represent a synthetic example of performing inversion using anapproximation to the objective function in which the seismic sources inthe measured data are encoded then summed; see U.S. ApplicationPublication No. 2010-0018718 by Jerome Krebs et al. This approximationspeeds up the inversion, because the encoded objective function can beevaluated using one run of the simulation software rather than runningit once for each source as is the case for conventional inversion. FIG.2 is a self-explanatory flow chart that focuses FIG. 1 on thisparticular embodiment, with step 210 showing the encoding approximation.

The geophysical properties model in this example is just a model of theacoustic wave velocity. FIG. 3 shows the base velocity model, i.e., the“unknown” model that will be inverted for and which was used to generatethe data to be inverted). for this example. The shading indicates thevelocity at each depth and lateral location, as indicated by the “color”bar to the right. FIG. 4 shows the inversion resulting from applicationof this invention as summarized by the flow chart in FIG. 2. In thisexample the sources are encoded by randomly multiplying them by eitherplus or minus one. The encoding of the sources is changed, in step 260,by changing the random number seed used to generate the codes used toencode the sources. Note the good match to the base model shown in FIG.3.

FIG. 5 shows the result of applying the inversion method outlined in theflowchart in FIG. 2, but eliminating the inventive feature of step 260.Note the inversion in FIG. 5 is dominated by crosstalk noise (thespeckled appearance of the inversion), whereas this crosstalk noiseartifact is largely invisible in the inversion resulting from thepresent invention (FIG. 4).

Encoding of simultaneous sources was previously disclosed (and claimed)in U.S. Application Publication No. 2010-0018718 by Jerome Krebs et al.along with the technique of varying the encoding from one iteration tothe next; see paragraph 62 and claim 3 in that patent publication.However, U.S. Application Publication No. 2010-0018718 by Jerome Krebset al. neither appreciates nor discloses that the encoding invention isa specific example of the generic invention disclosed herein.

Test Example 2 Approximation that Generates an Artificial Reflection

FIGS. 6-9 illustrate a synthetic example of performing inversion usingan approximation to the simulator that generates an artificialreflection. An example of such an approximation is using a finitedifference simulator such that the size of the cells in the grid arechanged with depth from the surface. This approximation speeds up theinversion, because the grid in the simulator could be adjusted tooptimize it in a depth varying manner. Typically smaller grid cells arerequired for the shallow portion of a finite difference simulator thanare required deeper in the model. The artifact generated by thisapproximation is an artificial reflection at the boundaries betweenchanges in the grid cell size.

FIG. 6 is a flow chart for the embodiment of the present inventionillustrated in this example. In this example, a variable grid simulatorwas not actually used to generate the artificial reflector. Instead(step 610) an artificial reflection is generated by placing a fictitiousdiscontinuity in the density model at 500 meters depth. Thisdiscontinuous density model was used by the simulator for modelupdating, but a constant density model was used to generate the measureddata (630 in FIG. 6). Inversion is then performed in a manner such thatonly the velocity model is updated (640), so that the fictitious densitydiscontinuity remains throughout the iterations of inversion.

The geophysical properties model in this example is just a model (620)of the acoustic wave velocity. FIG. 7 shows the base velocity model (themodel that will be inverted for and which was used to generate the datato be inverted) for this example. The shading indicates the velocity ateach depth. FIG. 8 shows the inversion resulting from application of thepresent invention as summarized by the flow chart of FIG. 6. In thisexample, in step 660, the depth of the fictitious density contrast israndomly changed using a normal distribution centered on 500 meters andwith a variance of 100 meters. Note the good match to the base modelshown in FIG. 7. In FIGS. 7-9 and 11-13, velocity is plotted as adimensionless relative velocity equal to the inverted velocity dividedby an initial velocity, the latter being the starting guess for what thevelocity model is expected to be.

FIG. 9 shows the result of applying the inversion method outlined in theflowchart of FIG. 6, but eliminating the inventive feature that is step660. It may be noted that the inversion in FIG. 9 has a clearly visibleartificial reflection 910 at 500 meters depth, whereas this artificialreflection is largely invisible in the inversion that used the presentinventive method (FIG. 8).

Test Example 3 Random Subsets of Measured Data

FIGS. 10-13 represent a synthetic example of performing inversion usingan approximation to the measured data. An example of such anapproximation is using a subset of the measured data (1010 in FIG. 10).This approximation reduces the amount of measured data, which speeds upthe inversion, because the computational time of the inversion isdirectly proportional to the number of measured data. In a typicalinversion, all of the measured data are needed to maintain a highhorizontal resolution, and thus in typical practice this approximationis not used. The artifact generated by this approximation is footprintsin the inverted models caused by sparse source positions and degradationof the horizontal resolution. FIG. 10 is a flow chart that focuses thesteps of FIG. 1 on the embodiment of the invention used in this example.In this example, a subset of the measured data (1030 in FIG. 10) is usedin the inversion, e.g. a subset of 5 data among 50 measured data.

The geophysical properties model in this example is just a model of theacoustic wave velocity. FIG. 11 is the base velocity model (the modelthat will be inverted for and which was used to generate the data to beinverted) for this example. The shading indicates the velocity at eachdepth. FIG. 12 is the inversion resulting from application of thisinvention as summarized by the flow chart in FIG. 10. In this example,in step 1060, a subset of the measured data is randomly selected asinversion iteration increases. This results in a different subset of thedata being used in each iteration cycle. FIG. 12 shows a good match tothe base model shown in FIG. 11 using ten percent of the measured data.

FIG. 13 shows the results of applying the inversion method outlined inthe flowchart in FIG. 6, but eliminating the inventive,artifact-reducing step 1060. It may be noted that the inversion in FIG.13 has artificial footprints at deeper parts below 2000 meters and shortwavelength noises in the overall inverted model, whereas this footprintnoises are mitigated in the inversion using the present inventive method(FIG. 12), and the short wavelength noises are invisible.

It should be understood that the flow charts of FIGS. 2, 6 and 10represent examples of specific embodiments of the invention that isdescribed more generally in FIG. 1.

The foregoing patent application is directed to particular embodimentsof the present invention for the purpose of illustrating it. It will beapparent, however, to one skilled in the art, that many modificationsand variations to the embodiments described herein are possible. Allsuch modifications and variations are intended to be within the scope ofthe present invention, as defined in the appended claims. Personsskilled in the art will readily recognize that in practical applicationsof the invention, at least some of the steps in the present inventivemethod (typically steps 140-160, and often generating the model in 120)are performed on a computer, i.e. the invention is computer implemented.In such cases, the resulting updated physical properties model of thesubsurface may either be downloaded or saved to computer storage.

REFERENCES

-   1. Tarantola, A., “Inversion of seismic reflection data in the    acoustic approximation,” Geophysics 49, 1259-1266 (1984).-   2. Sirgue, L., and Pratt G. “Efficient waveform inversion and    imaging: A strategy for selecting temporal frequencies,” Geophysics    69, 231-248 (2004).-   3. Weglein, A. B., Araujo, F. V., Carvalho, P. M., Stolt, R. H.,    Matson, K. H., Coates, R. T., Corrigan, D., Foster, D. J., Shaw, S.    A., and Zhang, H., “Inverse scattering series and seismic    exploration,” Inverse Problems 19, R27-R83 (2003).-   4. Fallat, M. R., Dosso, S. E., “Geoacoustic inversion via local,    global, and hybrid algorithms,” Journal of the Acoustical Society of    America 105, 3219-3230 (1999).-   5. Berkhout, A. J., “Areal shot record technology,” Journal of    Seismic Exploration 1, 251-264 (1992).-   6. Krebs, Jerome et al., “Iterative Inversion of Data from    Simultaneous Geophysical Sources”, U.S. Patent Application    Publication No. 2010-0018718 (Jan. 28, 2010).-   7. Clapp, R. G., “Reverse time migration with random boundaries,”    SEG International Exposition and Meeting (Houston), Expanded    Abstracts, 2809-2813 (2009).

The invention claimed is:
 1. A method comprising: using an approximationin a computer implemented iterative geophysical data inversion, whereinthe approximation is other than source encoding, and the approximationis made in at least one of (i) processing or selecting measured data toinvert, or (ii) parameterization of a subsurface model, or (iii)simulation of synthetic data to compare to measured data; and varying,with the computer, the approximation in iterative cycles of theiterative geophysical data inversion, wherein the varying causes anartifact in updated subsurface models to not coherently add in leadingto a final subsurface model as the iterative geophysical data inversionprogresses.
 2. The method of claim 1, further comprising: identifyingthe artifact.
 3. The method of claim 1, wherein the varying comprisesselecting an aspect of the approximation that has an effect on theartifact, and varying the aspect.
 4. The method of claim 1, wherein theusing the approximation in the computer implemented iterativegeophysical data inversion comprises using a subset of measured data asthe approximation.
 5. The method of claim 4, wherein the varyingcomprises varying the subset of the measured data in the iterativecycles of the iterative geophysical data inversion.
 6. The method ofclaim 4, wherein the varying comprises randomly varying the subset ofthe measured data in the iterative cycles of the iterative geophysicaldata inversion.
 7. The method of claim 4, wherein the varying comprisesvarying the subset of the measured data.
 8. The method of claim 4,wherein the varying comprises randomly varying the subset of themeasured data.
 9. The method of claim 4, wherein the artifact isfootprints of source position in an inverted model.
 10. The method ofclaim 1, wherein the subsurface model is an acoustic wave velocitymodel.
 11. The method of claim 1, wherein the varying includes varyingthe approximation for every iterative cycle of the iterative geophysicaldata inversion.
 12. The method of claim 1, wherein the varying includesvarying the approximation for consecutive iterative cycles of theiterative geophysical data inversion.
 13. The method of claim 1, whereinthe approximation in the computer implemented iterative geophysical datais a subset of measured data.